Journal of Geosciences, 58 (2013), 21–47

DOI: 10.3190/jgeosci.132

Original paper

Geological position, mineral assemblages and contamination of
granitic pegmatites in the Moldanubian Zone, Czech Republic;
examples from the Vlastějovice region
Milan Novák*, Tomáš Kadlec, Petr Gadas
Department of Geological Sciences, Masaryk University, Kotlářská 2, 611 37 Brno, Czech Republic; mnovak@sci.muni.cz*
Corresponding author
Three groups of pegmatites distinct in their geological position, age, internal structure, mineral assemblages and chemical composition of minerals (tourmaline, amphibole, garnet, and biotite) were distinguished in the Vlastějovice region,
Moldanubian Zone: a) tourmaline-bearing pegmatites (Qz + Kfs + Pl + Bt + Ms + Tur) enclosed in the pre-Variscan
orthogneiss, b) contaminated amphibole-bearing pegmatites (Pl + Qz + Amp + Kfs + fluorite + allanite) hosted by the
Fe-skarn, and c) tourmaline-bearing pegmatites cutting paragneisses (Qz + Kfs + Pl + Bt + Ms + Ab + Tur + Grt) and the
Fe-skarn (Qz + Kfs + Pl + Bt + Tur ± Ab, Amp, Grt, elbaite). The pegmatites enclosed in the orthogneiss show simple
internal structure and mineral assemblages, together with low degree of tectonometamorphic overprint. The amphibole-bearing pegmatites, likely anatectic and related to the Variscan MP–HT regional metamorphism, are spatially restricted
to the Fe-skarn body and highly variable in shape, size, effects of in situ contamination by Ca, Fe ± F and REE from thehost Fe-skarn, and degree of hydrothermal overprint.
The tourmaline-bearing pegmatites related to the Variscan magmatic event cut different rocks (paragneisses, Fe-skarn
bodies) and belong to the Moldanubian rare-element pegmatite province. They show distinct degree of textural differentiation, geochemical fractionation and external contamination by Ca and/or Fe (Ca,Fe-rich Al-poor tourmalines) higher
in the less evolved pegmatite bodies in the Fe-skarn. The tourmaline-bearing pegmatites were evidently generated fromthe granite–pegmatite body in the footwall contact of the Fe-skarn. Degrees of the textural differentiation and geochemical fractionation of the individual tourmaline-bearing pegmatites are comparable to those of the respective parts ofthe parental Footwall granite–pegmatite body. This observation seems consistent with the model of sequential derivationof pegmatite melts from evolving parental granite. Primitive to highly evolved and usually B-rich pegmatites originatedduring the Variscan orogeny from the MP (~0.6–0.7 GPa) to the LP conditions (~0.2 GPa), and manifest that formationof various granitic pegmatites was an integral part of the tectonomagmatic evolution of the region.
Keywords: tourmaline, granitic pegmatites, Fe-skarn, Vlastějovice, Moldanubian Zone
Received: 7 January 2013; accepted: 15 March 2013; handling editor: S. Vrána

1. Introduction
Granitic pegmatites are widespread magmatic rocks in
the Moldanubian Zone of the Bohemian Massif, Czech
Republic, although volumetrically negligible. Several
classes, groups, types and subtypes of granitic pegmatites were recognized based on their geological position,internal structure, mineral assemblages and origin byČech et al. (1981), Čech (1985), Novák et al. (1992,2012), Novák (2005), and Novák and Cempírek (2010).
However, the authors used the different classification
schemes of granitic pegmatites relevant at the time (e.g.,
Vlasov 1952; Ginzburg et al. 1979; Černý 1991a; Černý
and Ercit 2005).
The Vlastějovice region (Fig. 1a) is characterized byabundant granitic pegmatite bodies with different shape,size, host-rocks, mineralogy and origin. They are wellaccessible in large quarries on the Holý vrch and Magdalena Fe-skarn deposits, as well as on outcrops in the

Sázava valley. The Vlastějovice pegmatites thus represent
a very good object for a case study of typical granitic
pegmatites of the Moldanubian pegmatite province in a
relatively small area.
Pegmatites in the Vlastějovice region were divided
into several groups and subgroups based on their mineral
assemblages, internal structure and degree of contamination. However, the detailed field and laboratory study by
the current authors in 2001–2012 have suggested that
only three principal groups of granitic pegmatites exist in
this region (Kadlec 2007a, 2009): (i) tourmaline-bearing
pegmatites enclosed in the orthogneiss, (ii) contaminatedamphibole-bearing pegmatites from the Fe-skarn, and(iii) tourmaline-bearing pegmatites cutting Fe-skarn andsurrounding paragneisses.
The amphibole-bearing pegmatites cutting the
Vlastějovice Fe-skarn and their minerals were studied bynumerous authors (e.g., Koutek 1950; Vavřín 1960, 1962;
Povondra et al. 1985; Žáček et al. 2003; Ackerman 2005;
www.jgeosci.org

Milan Novák, Tomáš Kadlec, Petr GadasŽáček 2007; Ackerman et al. 2007; Novák and Cempírek
2010 and references therein). On the other hand, common
simple tourmaline-bearing types cutting the paragneisses
and the Fe-skarn as well as those enclosed in the orthogneiss body were examined only exceptionally (Vavřín
1960; Staněk and Schnorrer 1983; Ackerman et al. 2007;
Kadlec 2007a, 2009).
In this paper we present data for all the main typesof Vlastějovice pegmatites, including descriptions of
their geological position, internal structure, mineral assemblages as well as chemical composition of selectedminerals, namely tourmaline, biotite, amphibole, andgarnet. Degrees of geochemical fractionation and external
contamination of the individual pegmatite groups as wellas their geological position in the tectono-metamorphic
evolution of the Moldanubian Zone (see Novák 2005,
2007; Novák and Cempírek 2010; Gadas et al. 2012) arealso discussed.

2. Geological background2.1. Tectono-metamorphic and magmatic
evolution of the Moldanubian Zone
The Moldanubian Zone, the highly metamorphosed
core of the Bohemian Massif, represents a crustal (andupper mantle) tectonic collage assembled during the
Variscan orogeny and modified by several events ofsuperimposed deformations and high- to low-grade
metamorphic recrystallizations. Several tectonic/lithological units were defined (e.g., Fuchs and Matura 1976;
Matte et al. 1990; Fiala et al. 1995; Schulmann et al.
2008). (i) Mid-crustal, amphibolite-facies Drosendorf
Unit is traditionally divided into the Monotonous andVaried groups. In addition to the dominant high-grade
paragneisses, the Varied Group contains numerous
intercalations/small bodies of amphibolites, marbles,
calc-silicate rocks, orthogneisses, quartzites and graphitic gneisses. The Monotonous Group is composed ofmigmatized sillimanite–biotite–cordierite paragneisseswith subordinate quartzites and amphibolites. (ii) The
bottom of the lower crustal/upper mantle Gföhl Unit isformed by MORB-like metabasites, overlain by mainly
anatectic orthogneisses (Cooke and O’Brien 2001;
Hasalová et al. 2008) and by HP granulites, enclosing
minor bodies of pyrope- and spinel-bearing peridotites, garnet pyroxenites and eclogites (e.g., Fiala et al.
1987; O‘Brien and Rötzler 2003). (iii) Allochthonous
segments of ancient crust in the Moldanubian Zone
are represented by the Dobra gneiss (1.3 Ga, Friedl etal. 2004) in Lower Austria and the Světlík orthogneiss(2.1 Ga, Wendt et al. 1993) in southern Bohemia. The
Kutná Hora and the Svratka units situated along the NE
to E border of the Moldanubian Zone (Fig. 1a) were22

correlated by Vrána et al. (2009) and Pertoldová et al.
(2010) with the palaeo-Variscan Orlice–Sněžník Unit in
the Polish Sudetes. The latter constituted an older frame
against which the Moldanubian complex was exhumed.
Two major Variscan tectono-metamorphic events affected the Moldanubian Zone (Finger et al. 2007). a) The
Moravo–Moldanubian MP–HT event at ~340–330 Ma
includes a polyphase metamorphic evolution. (i) A HP–
HT event in upper amphibolite to granulite facies at
Tmax. ~850–900 °C and Pmax. = 1.2–1.8 GPa was recordedin granulites and eclogites from the Gföhl Unit (e.g.
Carswell and O’Brien 1991; Janoušek and Holub 2007).
It was more or less overprinted during a rapid decompression by (ii) a MP–HT event at T < ~700 °C and P~0.4–0.6 GPa (e.g., Pertoldová et al. 2009). This stage
was very likely connected to partial melting of the rocks.
(iii) Contact (periplutonic) LP–HT metamorphism aroundgranitoid plutons (see below) affected their envelope.
b) The Bavarian LP–HT event occurred between 326 and315 Ma and was very likely restricted to the Bavarian
Moldanubicum (Finger et al. 2007).
The tectonometamorphic history of the MoldanubianZone was characterized by extensive Variscan igneous
activity at individual stages of the geodynamic evolution, i.e. between Late Devonian to Permian (see Holubet al. 1995; Finger et al. 1997; Timmerman 2008 foroverview). The chemistry of Variscan magmas haschanged during evolution: (i) subduction-related normal
and high-K calc-alkaline suites (~370–345 Ma) (Holub et
al. 1997a; Janoušek et al. 2000; Žák et al. 2011) through(ii) (ultra-) potassic, magnesium-rich quartz syenitic tomelagranitic plutons – durbachites (Holub 1997) following shortly after exhumation of the high-grade Gföhl
Unit to mid-crustal levels (at ~340–335 Ma – Holub et
al. 1997b; Kröner et al. 2000; Janoušek and Holub 2007;
Kusiak et al. 2010; Kotková et al. 2010), and (iii) moderately–strongly peraluminous anatectic granites formed
as a consequence of the LP–HT metamorphic event at
331–326 Ma (the Eisgarn and Weinsberg suites) intruding the Moldanubian Zone, and (iv) late small plutons
of fine-grained I-type granitoids associated with minor
diorites at 319–300 Ma (e.g. Liew et al. 1989; Vellmer
and Wedepohl 1994; Holub et al. 1995; Gerdes et al.
2000, 2003).

2.2. Review of granitic pegmatites
from the Moldanubian Zone
2.2.1. Classification
Numerous granitic pegmatites are widespread throughout
the Moldanubian Zone. The following groups were distinguished (modified from Novák 2005 and Novák andCempírek 2010).

Granitic pegmatites from Vlastějovice, the Moldanubian Zone

a)

PRAHA

TH

XO

SA

Cretace
ous b
a

N

GIA

IN
UR

PL
TE

IAN U
AND
R
R
A
Á–B

N IT

N

sin

KHU
SU

BRNO

CZ

Monotonous andVaried groups.

ECH RE
AUSTR PIA

Gföhl Unit
KHU

SU

Kutná Hora and Svratka units
Arc-related magmatic rocks
N

R

M

A

GE

(Ultra)-potassic magmatic rocks

WIEN

Y

Anatectic granites

50 km

Vlastějoviceb)Fig. 1 Geological sketch maps of
the Moldanubian Zone in the Bohemian Massif (a) and Vlastějovice
region (b). B – Březina pegmatite,
N – Nosatá skála pegmatite, H –Holý vrch deposit, M – Magdalena
deposit (modified from Koutek
1950).

Sázava riverNB(i) Rare pre-Variscan (metamorphosed) pegmatites
are represented by small, simply zoned, coarse-grained
pegmatite-like nests (biotite + muscovite + oxy-schorloxy-dravite) in Ordovician orthogneisses (Vrána and
Kröner 1995; Povondra and Vrána 1996; Breiter et al.
2005a). They are developed at some localities (e.g.,Přibyslavice, Uhelná Příbram, Bechyně, Křížová hora,M

H
Fe-skarn

Vlastějovice

orthogneisscalc-silicate rockamphibolite
biotite paragneiss
locally migmatized

0.5 kmVlastějovice); however, these pegmatites were only
exceptionally studied (Novák 1981; Staněk and Schnorrer 1983; Povondra et al. 1987; Povondra 1989; Kadlec
2007a) and the age was not confirmed by radiometricdating. Furthermore, in the Přibyslavice orthogneisssome pegmatites are evidently post-tectonic and postmetamorphic (Povondra et al. 1987, 1998; Novák and23

Milan Novák, Tomáš Kadlec, Petr Gadas

Cempírek 2010; Bačík et al. 2013), and Variscan age ofat least part of these pegmatites is very likely. Except for
the Přibyslavice and Hamry nad Sázavou pegmatites they
have not been examined in detail.
(ii) Anatectic pegmatites (abyssal class sensu Černý
and Ercit 2005; anatectic pegmatites sensu London 2008),
include several distinct pegmatite groups. a) Dumortierite-bearing dikes (dumortierite + schorl + olenite ± foitite,garnet, kyanite) are enclosed in high-grade metamorphic
rocks (Vrána et al. 2009) and occur almost exclusively
along NE to E extremity of the Moldanubian Zone,
mainly in the adjacent Kutná Hora Unit (Cempírek andNovák 2006; Cempírek et al. 2006; Vrána et al. 2009)
and, less commonly, in the Gföhl Unit – Vémyslice
near Moravský Krumlov (Cempírek and Novák 2004).
b) Borosilicate-bearing pegmatite veinlet (grandidierite–ominelite + boralsilite + werdingite + dumortierite +schorl) cuts leucogranulite of the Bory Granulite Massif,
which post-dated the development of foliation in the hostgranulite at T ~ 750 °C and P ~ 0.6–0.8 GPa (Cempírek et
al. 2010). c) Coarse-grained, cordierite-rich leucosomes(cordierite + biotite + schorl-dravite ± dumortierite) occur
in migmatized gneisses of the Bory Granulite Massif andlocally show pegmatitic textures (Povondra et al. 1992).
d) Simply zoned, common (likely anatectic) pegmatites
with accessory andalusite and cordierite are abundant
mainly in the Strážek Moldanubicum, which mostly
show transitional (diffuse) contacts to their country
rocks (migmatized gneisses and granulites) and locallycontain large crystals of smoky quartz, feldspars, muscovite and tourmaline (schorl, oxy-schorl, dravite, foitite,magnesio-foitite) typically developed in pockets (Gadas
et al. 2012; Novák et al. 2004; Povondra 1981). e) Common pegmatites (sensu London 2008) are enclosed in avariety of rocks; anatectic origin is very likely. Where
the host rocks have contrasting chemical composition,
the pegmatites may have undergone a variable degreeof in situ contamination (e.g., diopside pegmatites frompyroxene gneisses and marbles, scapolite pegmatites inmarbles, amphibole-allanite pegmatites from Fe-skarns;
Novák 2005). Most anatectic pegmatites are spatiallyrelated to the Gföhl Unit.
(iii) Pegmatites of rare-element class are the mostabundant and exhibit high variability in shape, size, textures, degree of fractionation and mineralogy. They aresimple barren to highly fractionated with LCT, NYF and/or MIXED geochemical signature (see Černý and Ercit
2005; Černý et al. 2012). The rare-element granitic pegmatites of the Moldanubian Zone could be sub-divided
into four groups (a–d) according to their geochemicalaffinity (family) and P–T conditions.
a) Pegmatites of the LCT family are typically enrichedin B with tourmaline (schorl, oxy-schorl, dravite, foitite,
fluor-elbaite, elbaite, fluor-liddicoatite, rossmanite,
24

darrellhenryite; e.g., Povondra et al. 1985; Novák andPovon­dra 1995; Selway et al. 1998, 1999; Novák et al.
1999a, 2012, in print; Novák and Taylor 2000) as anomnipresent accessory to minor mineral. Less evolved
common pegmatites are characterized by the presenceof dravite, oxy-dravite, oxy-schorl to schorl (Novák etal. 2004), locally andalusite, cordierite and garnet. Morefractionated beryl-type pegmatites, locally with some accessory minerals (oxy-schorl, schorl, dravite, oxy-dravite,
beryl, fluorapatite, niobian rutile, ilmenite, monazite(Ce), xenotime-(Y), zircon, cordierite, garnet, columbite–tantalite, Y,REE-oxide minerals; e.g., Povondra 1981;Černý et al. 1997, 2000, 2007; Novák et al. 2004, 2008;
Breiter et al. 2005b; Škoda et al. 2011), are less abundant
than the more evolved complex pegmatites (Li-bearing;
Li-micas > Li-tourmalines > amblygonite > petalite; Povondra et al. 1985; Němec 1989, 1990; Černý et al. 1995,
2003; Teertstra et al. 1995; Novák et al. 1999b, 2013),
some with variety of accessory minerals (see Novák andCempírek 2010 and references therein). Their mineral
assemblages with common andalusite, sekaninaite andpetalite suggest an emplacement and crystallization at
P < ~0.2–0.3 GPa. Nevertheless, based on fluid-inclusions
study, Ackerman et al. (2007) suggested P = 0.31–0.43
GPa for the elbaite-subtype pegmatite from Vlastějovice.
Parental granites of the rare-element (LCT) pegmatites
are not known; nevertheless, tourmaline-bearing leucogranites (e.g., Buriánek and Novák 2004, 2007) closely
associated with durbachites were proposed as probablesource.
b) Some mostly “stockscheider-type” marginal pegmatites (LCT family), locally with beryl and Be-phosphates,
are related to Eisgarn granite and chiefly to highly
evolved granites of the Moldanubian Batholith near
Lásenice and Horní Stropnice (e.g, Kostelní Vydří, Homolka, Šejby; Breiter and Scharbert 1995; Cempírek et
al. 1999; Pavlíček et al. 2009).
c) Intragranitic pegmatites of NYF family (Škoda etal. 2006; Škoda and Novák 2007; Novák and Filip 2010;
Novák et al. 2011, 2012) occur exclusively in the Třebíč
Pluton, western Moravia, and in the Čertovo břemeno(Milevsko) Pluton, southern Bohemia. Both plutons
form large syn-exhumation tabular bodies (Dobeš andPokorný 1988; Žák et al. 2005) interpreted as a productof mixing between enriched mantle-derived magma
and a crustal melt (Holub 1997; Janoušek et al. 2000;
Janoušek and Holub 2007). Typical minor to accessory
minerals of pegmatites include common phlogopite,
allanite-(Ce), tourmaline (dravite, schorl, fluor-schorl;
Novák et al. 2011), aeschynite- and euxenite-groupminerals, titanite, ilmenite, actinolite, and rare beryl.
Recently, thin pegmatite dikes with analogous mineral
assemblages were found in the Tábor Pluton (Dražičky
SW of Tábor).

Granitic pegmatites from Vlastějovice, the Moldanubian Zoned) Merely the Li-bearing pegmatite from Kracovice
near Třebíč is considered to belong to the MIXED family(Novák et al. 2012). It contains, along with Li-bearing
minerals (Li-micas, Li-tourmalines), also common topaz, Y-bearing spessartine and Y,REE-oxide minerals(fergusonite, samarskite, pyrochlore). Also Drahonín
III and IV pegmatites near Strážek with tourmaline,
sekaninaite, beryl, Y-rich spessartine and Y,REE-oxideminerals (Škoda and Novák 2004) may belong to the
MIXED family.
Rare-element (LCT) granitic pegmatites from Bavarian
Moldanubicum (e.g., Hagendorf, Zwiesel, Pleystein; e.g.,
Mücke et al. 1990; Dill et al. 2012 and references therein)with abundant primary Fe,Mn-phosphates but rare tourmaline are very likely related to the granites dated at
326–321 Ma (Siebel 1995; Chen and Siebel 2004; Gerdes
et al. 2003; Finger et al. 2007 and references therein).
However, there are no analogical occurrences known
from the territory of Czech Republic. Also rare granitic
pegmatites in the Austrian part of the Moldanubian Zone,
where Li-bearing pegmatites with Li-tourmalines andscarce Li-micas were found (Ertl et al. 2004, 2005, 2012),
are not discussed.
(iv) Pegmatites of miarolitic class are very rare andonly some intragranitic NYF pegmatites enclosed in theČertovo břemeno Pluton, central Bohemia (Kovářov,Vepice; Škoda et al. 2004) and from the Třebíč Pluton(Velké Meziříčí, Novák and Cempírek 2010; A. Zachař
pers. comm. 2012) closely spatially and mineralogicallyrelated to the above NYF pegmatites of rare-elementclass show typical features of miarolitic pegmatites –large pockets with crystals of smoky quartz, feldspars
and titanite, and close relationship to the parental granite.
Small miarolitic (LCT) pegmatites exceptionally occur
also in anatectic granites (Eisgarn) of the Central Moldanubian Pluton (Telč region).

2.2.2. Geochronology
The radiometric ages (U–Pb monazite, U–Pb columbite)of the individual pegmatite groups were only scarcely
published. (i) We do not have any data from metamorphosed pegmatites; however, they are expected to be
Ordovician as their parental orthogneisses are (Vrána
and Kröner 1995). (ii) The age of anatectic pegmatites
is also uncertain. Their relations to the MP–HT regional
metamorphism and anatexis, and the absence of evident
metamorphic overprint, suggest that they are mostly Variscan but some might be older. (iiia) The pegmatites of
the rare-element class (LCT) crystallized in a short periodof ~340–332 Ma (Novák et al. 1998; Ertl et al. 2004;
Melleton et al. 2012), although new data also indicate
the age of emplacement of some Li-bearing pegmatites
at ~325 Ma (Melleton et al. 2012). (iiib) The pegmatites

related to the Moldanubian Batholith including their
miarolitic relatives were younger; they have been dated
at ~320 Ma (whole rock Rb–Sr; “stockscheider-type”;
Breiter and Scharbert 1998) and 331–326 Ma (the Eisgarn
and Weinsberg suites), respectively. (iiic) The intragranitic NYF pegmatites of the Třebíč, Čertovo břemeno
and Tábor plutons as well as their miarolitic relatives(iv) were not dated radiometrically but the ages of theirparental granites of ~340–335 Ma (Holub et al. 1997b;
Janoušek and Gerdes 2003; Kotková et al. 2010; Kusiak
et al. 2010) suggest the formation in the same period as
the LCT pegmatites given above and support orogenic
origin of these NYF pegmatites (Černý et al. 2012; Novák
et al. 2012).

2.3. Geological setting of the Vlastějovice
regionThe Vlastějovice locality is situated in the Ledeč–Chýnov
belt of the Varied Group (Drosendorf Unit), MoldanubianZone, along the border with the Kutná Hora Unit (Fig.
1a). Dominant two-mica paragneisses to locally migmatized biotite–sillimanite paragneisses contain common
intercalations of amphibolite, pyroxene gneiss, quartzite,
marbles, biotite to two-mica tourmaline-bearing ortho­
gneisses and rare eclogite (Breiter et al. 2005a), which
are spatially associated with large bodies of Fe-skarn. The
regional metamorphic foliation trends NE–SW and dipsat moderate to steep angles to the NW. Several lenticularbodies of Fe-skarns, up to several tens of meter thick andseveral hundreds of meter long, occur in the NE–SW
trending synclinal structure at Vlastějovice building theHolý vrch and Magdalena Fe-skarn magnetite deposits(Fig. 1b; Koutek 1950; Potužák 1996). The contacts of
the Fe-skarn are generally parallel to the foliation of thehost gneisses. Small bodies of leucocratic granites andsimple tourmaline-bearing pegmatites are common in thisregion as well (Kadlec 2009).
Biotite to two-mica orthogneisses form a NE–SW
elongated body, 3.5–0.5 km in diameter, located Nof Vlastějovice (Fig. 1b). This body is a member of adiscontinuous belt of orthogneisses (Klečka et al. 1992;
Breiter et al. 2005a) including the Přibyslavice orthogneiss. The Vlastějovice orthogneiss is a medium-grainedrock with moderate foliation and mostly tectonic contacts with the adjacent Fe-skarn. The contact was modified locally by intrusion of a footwall granite–pegmatite.
Chemical composition of the orthogneiss is given in
Tab. l. Orthogneiss body contains several simple pegmatites with minor to accessory biotite, muscovite, andtourmaline.
The Fe-skarn bodies in Vlastějovice are highly heterogeneous, consisting of grossular-andradite > hedenbergite > diopside > magnetite > epidote. Minor to25

Milan Novák, Tomáš Kadlec, Petr Gadas

Tab. 1 Chemical compositions of rocks from Vlastějovice (wt. %)
1

2

3

4

5

6

7

FGM29

V8

FGM28

V13

VLS-1

VLS-2

VLS-3

SiO2

74.34

71.19

73.55

43.26

40.77

40.11

41.79

TiO2

0.02

0.16

0.17

0.82

0.44

0.59

0.27

Al2O3

15.51

13.30

16.18

12.36

9.94

10.24

1.51

Fe2O3

0.34

0.13

1.46

4.74

20.69

13.89

19.11

FeO

–

1.75

–

11.76

–

–

–

MnO

0.01

0.03

0.03

0.40

0.79

0.51

0.35

MgO

0.01

0.37

0.24

2.00

2.17

2.60

5.21

CaO

0.88

1.30

0.96

14.48

24.04

31.01

29.97
0.09

Na2O

4.90

1.17

3.12

2.46

0.34

0.19

K 2O

3.80

8.34

5.45

2.71

0.02

0.03

0.01

P 2O 5

0.00

0.28

0.23

0.23

0.14

0.14

0.20

H 2O

–

0.47

–

0.94

–

–

–

LOI

–

1.18

–

2.96

0.50

0.60

1.14

Sum

99.81

99.67

101.39

99.12

99.84

99.91

99.65

1 – orthogneiss, 2 – orthogneiss (Syka 1990), 3 – Footwall granite–pegmatite (granite I), 4 – amphibole-rich pegmatite (Syka 1990), 5, 6, 7 – Fe-skarn

accessory minerals include amphibole, biotite, calcite,
quartz, allanite-(Ce), plagioclase, K-feldspar, scapolite,
hematite, titanite, apatite, and fluorite. The following
rock types were distinguished: (i) very abundant skarn
s.s.: monomineralic massive garnetite and banded garnet–clinopyroxene rock commonly forming central partsof the Fe-skarn bodies; (ii) minor clinopyroxene–garnet–epidote rock; (iii) lenses of massive magnetite, up
to several m in diameter; (iv) hybrid rock (hastingsite +almandine + biotite + quartz + K-feldspar + plagioclase)
forming a zone, a few decimeters to several meters
thick, located between the Fe-skarn and the surrounding
orthogneisses. The chemical analyses of various typesof Fe-skarns are given in Tab. 1. The Fe-skarns wereregionally metamorphosed at T ~590–680 °C and P~0.45–0.65 GPa, corresponding to the (ii) MP–HT Variscan metamorphic event (Žáček 1997). Several typesof hydrothermal mineralization cutting the Fe-skarn
form veins and pods, up to several dm thick: calcite +apophyllite, quartz + prehnite + apophyllite, datolite+ prehnite, fluorite + calcite (Tvrdý 2000; Žáček and
Fišera 2001; Kadlec 2007b, 2012). Rare quartz–calcite
veins with antimony mineralization (dominant berthierite) are mostly bound to steep S–N trending mylonite
zones (Koutek and Žák 1953; Brabec 2002).

3. Experimental methods

3.1. Electron microprobe
Tourmaline, garnet, amphibole, micas, plagioclase andsome associated minerals were analyzed by an electron
microprobe Cameca SX 100 at the Joint Laboratory of
26

Electron Microscopy and Microanalysis, Departmentof Geological Sciences, Masaryk University, Brno and
the Czech Geological Survey, Brno in a wavelengthdispersive mode and with accelerating voltage of 15
kV, beam current of 10–20 nA and spot size of 1–5 μm.
The following X-ray lines and standards were used:
K α: sanidine (Si, Al, K), albite (Na), olivine (Mg),andradite (Ca, Fe), rhodonite (Mn), hornblende (Ti),chromite (Cr), topaz (F), ZnS (Zn), NaCl (Cl), apatite(P) and Ni (Ni); Lα: YAG (Y) and Lβ: benitoite (Ba).
The raw data were reduced using PAP matrix corrections (Pouchou and Pichoir 1985). The crystal-chemical
formulae of tourmaline were calculated based on thegeneral formula XY 3Z6T6O18(BO3)3V3W, where X = Na,
Ca, K, vacancy; Y = Fe, Mg, Mn, Ti, Al, Li; Z = Al,
Fe, Mg, Cr; T = Si, Al, B; B = B; V = OH,O; W = OH,
F,O (see Henry et al. 2011). The Z-site was considered
to be occupied by Al and Mg, Fe tot as FeO. Normalization to Si = 6 apfu was chosen because of the absenceof Fe 2+/Fe 3+ measurements in black tourmaline andelevated contents of Li in tourmalines from the Elbaite
pegmatite (Povondra et al. 1985). The crystal-chemical
formulae of garnet were calculated from EMPA dataand normalized to 8 cations and 12 oxygens whereby
Fe was split to Fe 3+ or Fe2+ according to the stoichiometry. The crystal-chemical formulae of amphibole andbiotite were obtained based on 24 anions or 12 anions(O,OH,F) respectively, assuming that all Fe is divalent
in both cases. The crystal-chemical formulae of feldspars were calculated based on 8 oxygens. Calculationsof Mg/(Mg + Fe) values in tourmaline, amphibole andmica were done using total Fe as FeO tot, disregarding
its potential valence and distinct position in the crystal structure of minerals. All mineral abbreviations inGranitic pegmatites from Vlastějovice, the Moldanubian Zone

tables, figures and in the text were taken from Whitney
and Evans (2010).

3.2. Whole-rock geochemistry

biotiteapatitetourmaline
muscovite
orthogneissdiffuse contact

The bulk compositions of Fe-skarn were determinedat the Acme Chemical Laboratories Ltd., Vancouver,
Canada, by using ICP-ES after they were melted withlithium borate. Trace elements were analyzed by ICP-MS
following a lithium tetraborate fusion. See http://www.
acmelab.com for further details.

pegmatite

50 cm
4. Geological setting, internal
structure and mineral assemblages of
the Vlastějovice granitic pegmatites
Granitic pegmatites from the region were divided into
three distinct groups based on their likely parental magmatic rock, internal structure, shape and size of bodies,mineral assemblages and degree of host-rock contamination (Kadlec 2007a, 2009; Novák and Cempírek 2010).

4.1. Tourmaline-bearing pegmatites fromorthogneiss
Several elongated pods, up to ~0.5–1.5 m long and up
to 0.5 m thick, were found in the Holý vrch quarry.
Pegmatite pods show transitional contacts and theirelongation is often concordant with the foliation of thehost orthogneiss (Fig. 2). However, this foliation does
not continue into the coarse-grained pegmatite. Fragmentation of elongated tourmaline crystals and their
healing is common. The pegmatites (Qz + Kfs + Pl) aresimply zoned showing increasing grain size from thecontact inwards and locally small quartz core. Biotite,abundant in outer parts of pegmatite pods, mostly predominates over prismatic crystals of black tourmaline(dravite, schorl), up to 10 cm long, more common in
the center. Large flakes of muscovite and small grainsof green fluorapatite are frequent but other accessory
minerals, such as zircon, are rare (Kadlec 2007a).
Staněk and Schnorrer (1983) described also phenakite
and buergerite from this type of pegmatite; however,Fig. 2 Idealized cross section through pegmatite in orthogneiss (modified from Kadlec 2007a).

determination of buergerite is not unequivocal and its
presence seems very unlikely.

4.2. Amphibole-bearing pegmatites
Contaminated, amphibole-bearing pegmatites (barren
pegmatites according to Ackerman et al. 2007) are very
common and about 100 dikes were mentioned by Vavřín
(1960, 1962), Ackerman et al. (2007), Kadlec (2007a,2009) and Novák and Cempírek (2010). They are randomly distributed within the whole Fe-skarn body (Fig.
3a–b), although we have never found them in the hybrid
rock. Based on major and minor minerals (Tab. 2), degreeof hydrothermal overprint and presence or absence of
pockets, four major subtypes were recognized, as follows.
(i) Ordinary amphibole-bearing pegmatites (Pl+ Qz + Kfs + Amp) are by far the most abundant but
also quite variable in size, shape, thickness of reaction
rims and proportion of the individual minerals (Vavřín
1962; Novák and Hyršl 1992; Žáček et al. 2003). They
form elongated dikes to irregular intrusive bodies (Figs
3b, 4) commonly several dm thick and several m long
(Fig. 3b–d); the largest dike was ~1.5 m thick. Theycut exclusively the Fe-skarn with irregularly developed
reaction zones (Fig. 4). Abundant reaction rims, up to
30 cm thick, consist of dominant amphibole and locallyalso fluorite, biotite and a relatively Ca-rich plagioclase(An06–35) compared to that from the central portions ofTab. 2 Mineral assemblages of amphibole-bearing pegmatites
Pegmatite subtype
ordinary pegmatites
fluorite-rich pegmatites
pegmatites with hydrothermal overprint
pocket pegmatite

Major minerals
Pl > Qz, Kfs, Amp
Pl > Fl > Kfs, Qz, Amp
Pl > Kfs, Qz, Fl
Pl > Kfs, Qz, Ab, Pl

Minor minerals
Fl, Aln, Bt, Hd, Grt
Bt, AlnAmp, Prh, Apo, Ep, Bt
Fl, Bt, Amp

Accessory minerals
Ttn, Cal, Mag, Ax, Py, Po, Wo
Ttn, Mag
Ttn, Aln, Grt, Cal, Tur, Opl
Aln, Cal, Apo, phenakite

Products of hydrothermal alteration of allanite-(Ce) in most dikes disregarding the subtype include: bastnäsite-(Ce) >> thorogummite, ancylite,
brockite, parisite-(Ce), rhabdophane-(Ce) (Goliáš 2002); further accessory minerals in amphibole-bearing pegmatites: celadonite, fluorapatite,uraninite, thorite, pyrochlore-supergroup mineral, bismuth, bismuthinite (e.g., Rezek and Krist 1985; Goliáš 2002).

27

Milan Novák, Tomáš Kadlec, Petr Gadas

a

b

c

d

Fig. 3 Amphibole-bearing pegmatites in Fe-skarn: a – view on the Holý vrch quarry, Vlastějovice, note Pegmatite No. 12 in the upper left part of
the quarry, several outcrops of Footwall granite–pegmatite (light areas), and amphibole-bearing pegmatites in the upper right part of the quarry;b – amphibole-bearing pegmatite dikes cutting the Fe-skarn; c – crossing of amphibole-bearing (subhorizontal) and tourmaline-bearing pegmatite(subvertical); d – detail of amphibole-bearing pegmatite dike ~25 cm thick. Field situation on 31 August 2010 (a) and on 28 March 2009 (b to d);photo M. Novák.			

pegmatite (An00–20; Ackerman et al. 2007). The pegmatites
are coarse-grained, commonly with subhomogeneousinternal structure (Fig. 3d), and contain locally abundantamphibole > fluorite > biotite >> hedenbergite > andradite–grossular ~ allanite ~ epidote ~ titanite ~ calcite ~magnetite (the most common order) along with dominantplagioclase, quartz and locally also abundant K-feldspar(Tab. 2). Very rare axinite-(Fe) and tourmaline were also
identified. Monomineralic grey quartz forms locally irregular masses and veins located often along the contact
with the host skarn, enclosing its fragments. Black togreen-black amphibole (hastingsite to ferro-edenite)
is present as euhedral to subhedral phenocrysts, up to~10 cm in size, and massive, coarse-grained aggregates(Žáček and Povondra 1991; Žáček 2007). Common
allanite-(Ce) present in amphibole-bearing pegmatites
and scarcely in host Fe-skarn is often replaced by secondary fluorcarbonates (e.g., bastnäsite; Tab. 2), particularly28

if associated with fluorite (Goliáš 2002). Subhedral toeuhedral crystals of yellowish-brown Al-rich titanite,less than 1 cm across, occur in black hastingsite andfluorite, chiefly from reaction zones between pegmatiteand skarn (Mrázek and Vrána 1985). Abundant to scarce,dark violet, purple to rarely colorless fluorite forms
coarse-grained aggregates, up to several dm in size, inthe pegmatite or in the exocontact zone. Fluorite locally
predominates over quartz and feldspars. It is closely
associated with allanite with deep violet to black rims
around allanite grains. Ackerman (2005), based on the
REE-geochemistry and fluid inclusion study, suggested
that the fluorite crystallized during the magmatic–hydrothermal transition. Also wollastonite, chlorite, andpyrite occur in minor amounts mostly in marginal partsof the pegmatite dikes (e.g., Vavřín 1960, 1962; Žáček
and Povondra 1991; Novák and Hyršl 1992; Žáček et al.
2003; Houzar et al. 2009).

Granitic pegmatites from Vlastějovice, the Moldanubian Zone(ii) Fluorite-rich, amphibole-bearing pegmatite
dikes are relatively common only in the Magdalena Feskarn body. They form thin (up to 30 cm thick) elongated,vertical and locally asymmetric dikes, where fluorite isconcentrated to the upper zone adjacent to contact. Reaction rims are negligible. Biotite is more abundant thanin the ordinary amphibole-bearing pegmatites (Tab. 2).
(iii) Amphibole-bearing pegmatites with significant
hydrothermal overprint and small pockets are very
similar to the ordinary amphibole-bearing pegmatites ininternal structure and primary mineral assemblages except for almost total absence of biotite in this pegmatite
type. Hydrothermal minerals prehnite and apophyllite are
typically present in small pockets enclosed in K-feldspar
associated with fluorite. Minor calcite, garnet, titanite,allanite, epidote, opal, and very rare fibrous tourmaline,
pyrite, and bastnäsite were also identified in this assemblage (Tab. 2). Several pegmatite dikes occur exclusively
in the upper part of the Magdalena Fe-skarn body.
(iv) Amphibole-bearing pegmatite with a large
pocket (~1 m3) was described by Vavřín (1960), Čujan
(1966) and Kadlec (2010) from the Magdalena Fe-skarn
quarry. The zoned dike, ~2 m thick, consists of outeroligoclase-rich unit and blocky K-feldspar with quartz
in the core. The mineral assemblages also include amphibole, fluorite, biotite, and rare allanite. In the pocket,
crystals of smoky quartz (up to 60 cm long), orthoclase,
albite, calcite, apophyllite, phenakite, and clay minerals
were identified (Kadlec 2010).
Crosscutting dikes of ordinary amphibole-bearing andtourmaline-bearing pegmatites described below havebeen found only recently (Fig. 3c), and show unambiguously that the former crystallized earlier than the latter(see also Čech 1985; Novák 2005; Ackerman et al. 2007;
Novák and Cempírek 2010). The P–T conditions of theformation of amphibole-bearing pegmatites (600–640 °C
and 0.42–0.58 GPa) deduced from fluid inclusions (Ackerman et al. 2007) fall into the field of regional MP–HT
metamorphism of the host rocks (Žáček 1997). Chemicalcompositions of amphibole-rich and quartz-poor ordinary
amphibole-bearing pegmatites are given in Tab. 1.

4.3. Tourmaline-bearing pegmatites
4.3.1. Occurrences
Tourmaline-bearing pegmatites are rather common in
Vlastějovice; ~20 dikes were recognized including Libearing elbaite-subtype pegmatite studied by Čech (1985)
and Ackerman et al. (2007). They are concentrated in a
W–E trending belt exclusively in the central and easternpart of the Holý vrch quarry; they are not known from
the Magdalena Fe-skarn deposit. The pegmatites are

ENE

WSW

2m

Fe-skarnmagnetite

pegmatiteamphiboleFig. 4 Amphibole-bearing pegmatites cutting Fe-skarn (slightly modified
from Novák and Hyršl 1992).

evidently related to the granite–pegmatite body in the
footwall contact of the Fe-skarn (Figs 3a–5). In contrast
to the amphibole-bearing pegmatites from the Fe-skarn,
the tourmaline-bearing pegmatites were also found inparagneisses surrounding the Fe-skarn bodies (Kadlec
2007a, 2009). The pegmatites form NW–SE trending andsteeply dipping dikes and rarely irregular bodies, withhomogeneous to simply zoned internal structure (Kadlec
2007a, 2009; Novák and Cempírek 2010). Black to greyish black tourmaline forms solitary grains, coarse-grained
aggregates and quite commonly graphic intergrowths ofquartz + tourmaline, up to 10 cm in size. Six individual
pegmatite bodies and Footwall granite–pegmatite werestudied in detail. They represent typical examples of the
tourmaline-bearing pegmatites characterized by distinct
host rocks, degree of textural differentiation, geochemical
fractionation and external contamination.
The Březina pegmatite forms a lenticular body, up to
3 m thick and 10 m long, located ~2 km SW of the Holývrch Fe-skarn body. The pegmatite is heterogeneous,consisting of rather irregularly distributed patches of adominant medium- to coarse-grained unit (Qz + Kfs + Ab
+ Ms + Bt + Grt + Tur), blocky K-feldspar and massive
quartz (Tab. 3). The pegmatite is enclosed in migmatizedbiotite–sillimanite paragneiss with minor cordierite and ismostly concordant, only locally with discordant contacts
to the foliated host rock.
The Nosatá skála pegmatite, a dike up to ~5 m thickand several tens of m long, crops out ~ 1 km W of theHolý vrch Fe-skarn body. The pegmatite shows heterogeneous internal structure consisting of irregularly
distributed patches of a fine- to medium-grained unit
within the prevalent coarse-grained pegmatite (bothwith an assemblage Qz + Kfs + Ab + Bt + Ms; garnet
and tourmaline are more common in the coarse-grained29

Milan Novák, Tomáš Kadlec, Petr Gadas

a)
1.et.
2.et.
3.et.

Sps

No.12
4.et.

No.4

5.et.

FGP I

3.et.

No.12
Sps

4.et.

b)
5.et.

FGP III

No.4

15 m

gneisses, amphibolites

FGP II

Fe-skarnfootwall granite, pegmatites

Fig. 5a Schematic geological map of the Holývrch quarry. b – Cross section through the Fe-skarn, orthogneiss, Footwall granite–pegmatite
and related tourmaline-bearing pegmatites. FGP– Footwall granite–pegmatite – granite I, II and
III; Pegmatite No. 4; Pegmatite No. 12; Sps –Spessartine pegmatite.

Tab. 3 Mineral assemblages of tourmaline-bearing pegmatites and pegmatites in orthogneiss
Locality/reaction rims
Pegmatites in orthogneiss/absent
Pegmatite Březina/absent
Pegmatite Nosatá skála/absent

Proportions of minerals
Tur-common; Bt ~ Ms, Bt > Tur
Tur-common; Ms >> Bt,
Tur ~ Grt > Bt
Tur-common; Bt ~ Ms,
Tur > Bt > Grt

Accessory minerals
Ap, Zrn, phenakite
Ap, Zrn, Rt, Ttn, Xtm, Mnz, Py, Sil
Ap, Zrn, Rt, Ttn, Xtm, Mnz, Py, Dsp, Ilm

Footwall granite pegmatite/minor

Tur-very rare; Bt >>> Tur > Amp Ap, Py, Rt, Zrn, Aln, Ant, Bi-sulphide

Pegmatite No. 12/moderate

Tur-rare; Bt >> Tur ~ Amp

Ap, Ttn, Zrn, Py, Po, Aln, Cst, Rt, Fl

Pegmatite No. 4/minor

Tur-rare; Bt >> Tur > Amp

Ap, Ttn, Zrn, Py, Apy, Cal

Spessartine pegmatite/absent

Tur-rare; Bt > Tut > Grt

Elbaite pegmatite/absent (Čech 1985) Tur-common; Tur >> Bt

Ap, Ttn, Zrn, Py, Apy, Ep, Cal, Fl, Sp, Cst, Y-rich milarite, uraninite,
Nb-rich rutile, minasgeraisite-(Y), Sn-rich titanite
Ap, Fl, Zrn, Py, Cst, Mag, Elb, manganocolumbite, pyrochlore-groupminerals, danburite, datolite, bavenite, stokesite

Mineral assemblages from the authors’ observations including data of Staněk and Schnorrer (1983), Čech (1985) and Povondra et al. (1985).

30

Granitic pegmatites from Vlastějovice, the Moldanubian Zone

facies), blocky K-feldspar and massive quartz locallywith small pockets. The pegmatite discordantly cuts
pyroxene paragneisses with thin intercalations of calcite
marbles. Both the Březina and Nosatá skála pegmatites
show sharp contacts with the country-rock paragneisses
and no reaction rims.
The Footwall granite–pegmatite dike (Qz + Kfs + Pl+ Bt) occurs along the footwall contact of the Fe-skarnwith the underlying orthogneiss at Holý vrch (Figs 3a, 5,
6a–b, d). This complicated and tectonically fragmented
dike is at least ~250 m long and ~1 to ~10 m thick in theoutcrops (Fig. 5). The heterogeneous granite–pegmatite
body consists of three texturally different facies. A medium- to coarse-grained and locally porphyritic granite I
is located exclusively in the north-eastern upper cornerof the quarry. A coarse-grained, subhomogeneous granite
II, locally with anhedral grains of K-feldspar, occurs inthe southwestern part of the body (the lower part of thequarry). The most evolved and less abundant, coarsegrained granite III (Fig. 5), with large subhedral crystalsof blocky K-feldspar, locally up to 30 cm in size (Fig.
6e), cropped out in the centre of the quarry (Fig. 5).
Graphic intergrowths of Qz with Kfs are locally common in the granites II and III. The granitic rocks areoccasionally strongly altered to a mixture of clay minerals and quartz. Contacts with the host orthogneiss andFe-skarn are mostly sharp. Only exceptionally a reaction
zone with amphibole, up to 3 cm thick, occurs along thecontact with the Fe-skarn; however the contact was often
tectonically modified. Chemical analysis of the granite I
is given in Tab. 1.
The Pegmatite No. 12 was evidently derived from theleast evolved granite I (Figs 5, 6a). The pegmatite forms
a matrix of brecciated Fe-skarn with a complex morphology (Fig. 6a). The individual parts of the pegmatite
body are from several dm up to 1 m thick in the current
outcrops. A medium- to coarse-grained unit (Qz + Kfs+ Pl + Bt), with very rare tourmaline and amphibole,resembles the parental granite I as the typical pegmatitic
textures (e.g., graphic intergrowths Qz + Kfs) are absent.
This body exhibits reaction rims at the contact with thehost Fe-skarn and its enclaves, up to 10 cm thick, with
common greenish-black subhedral grains of amphibole,and locally rare pyrite, pyrrhotite, fluorite, allanite-(Ce)and other accessory minerals (Tab. 3).
Pegmatite No. 4 occurs as an elongated subhomogeneous dike, up to 1 m thick and ~20 m long (Fig. 6b),consisting exclusively of a coarse-grained unit (Qz +Kfs + Pl + Bt + Tur + Amp). Typical pegmatitic textures(e.g., graphic intergrowths) are rare. This pegmatite wasevidently derived from the granite II (Figs 5, 6b) and the
textures of the granite and pegmatite are mutually very
similar. The pegmatite shows sharp to locally transitional
contacts with the host Fe-skarn. The reaction zone is only

several mm thick (Fig. 6c) with more abundant biotite in
the adjacent pegmatite and rare amphibole at both endoand exocontacts with the Fe-skarn.
The elongated dike of the Spessartine pegmatite, up
to 0.5 m thick and ~15 m long, was evidently derived
from the most evolved granite III (Figs 5, 6d). It consists of a dominant coarse-grained unit (Qz + Kfs + Pl ±Tur) with only locally developed patches of graphic unit
(Kfs + Qz), blocky K-feldspars, small quartz core andmedium-grained albite. The latter contains small massesof fluorite and several accessory minerals including
abundant spessartine (Tab. 3). The pegmatite evolved tomassive quartz in the upper tip of the dike. Contact withthe host Fe-skarn is typically sharp; no reaction rims wereobserved in hand specimens (Fig. 6f).
Elbaite pegmatite occurred in the western part of theHolý vrch Fe-skarn body close to the Spessartine pegmatite. It was completely mined out in 1982 and its internal
structure and individual minerals were briefly described(Čech 1985; Povondra et al. 1985; Selway 1999; Ackerman et al. 2007). The pegmatite dike, up to ~2 m thick,exhibited simply zoned internal structure with a fine- tomedium-grained outer zone (Qz + Kfs + Pl ± Bt ± Tur),coarse-grained inner zone (Qz + Kfs + Pl + Tur) with
abundant graphic intergrowths (Qz + Kfs, Qz + Tur),blocky K-feldspar, albite, and rare pockets containing
crystals of albite, K-feldspar, smoky quartz and red fluorelbaite (Tab. 3). No samples from the contact with thehost Fe-skarn were available for our study; however, thecontacts were described as sharp (Čech 1985; P. Povondra
pers. comm. 2010).

4.3.2. Mineralogy
The tourmaline-bearing pegmatites always contain minor
to accessory biotite (Tab. 3). The amount of tourmalinevaries from a very rare to rare accessory mineral in the
Footwall granite–pegmatite and in the Pegmatite No. 12,
through an accessory phase in the Spessartine pegmatite
to a frequent (locally minor) mineral in pegmatites fromparagneisses and in the Elbaite pegmatite. Primary muscovite is common only in the pegmatite bodies hosted bygneisses but absent in all pegmatites cutting the Fe-skarn.
Amphibole is absent in all pegmatites from paragneisses,
Spessartine pegmatite and Elbaite pegmatite, it is rarein the Pegmatite No. 4 and Pegmatite No. 12 (Tab. 3).
Euhedral grains of garnet are abundant in both pegmatites
from paragneisses (Tab. 3) but absent in the bodies cutting the Fe-skarn except for the Spessartine pegmatite.
The assemblage of accessory minerals in the
tourmaline-bearing pegmatites is dominated by fluorapatite. Also magnetite, zircon, rutile, titanite,
monazite-(Ce), xenotime-(Y), allanite-(Ce), ilmenite,31

Milan Novák, Tomáš Kadlec, Petr Gadas

a

b

c

d

e

f

Fig. 6 Tourmaline-bearing pegmatites cutting the Fe-skarn: a – Footwall granite–pegmatite (granite I – right side) and Pegmatite No. 12 (left side);b – Footwall granite–pegmatite (granite II) and Pegmatite No. 4 up to 1 m thick; c – detail of the Pegmatite No. 4, about 30 cm thick, note thinreaction rim with amphibole in garnet skarn (left footwall); d – Footwall granite–pegmatite (granite III) and thin dike of the Spessartine pegmatite
up to 50 cm thick, marked by an arrow; e – large crystal of K-feldspar with grains of black tourmaline in the Footwall granite–pegmatite (graniteIII); f – detail of the Spessartine pegmatite, note sharp contacts. Field situation on 28 March 2009 (a), 19 January 2007 (b), 10 December 2004 (c),2 June 2009 (d), 6 July 2007 (e) and 31 March 2007 (f). Photo T. Kadlec.

320.104
0.667
0.013
0.216

31.334
3.830
0.170

Ca
Na
K
X
⁪

O
OH
F

* calculated by stoichiometry

0.029
5.631
2.478
0.758
0.020
0.000
8.916

0.127
6.512
1.206
1.320
0.010
0.000
9.175

Ti
Al
Fe2+
Mg
Mn
Zn
∑ Y+Z

30.855
3.766
0.234

0.253
0.675
0.009
0.063

6.000
3.000

6.000
3.000

Amp-bearing
pegmatite
1/1
34.81
0.22
10.08
27.72
17.19
2.95
0.14
b.d.l.
1.37
2.02
0.04
0.43
3.28
-0.18
100.07Si
B

sampleSiO2
TiO2
B 2O 3*
Al2O3
FeO
MgO
MnO
ZnO
CaO
Na2O
K 2O
F
H2O*
O=F
Total

Pegmatites
fromorthogneiss
56/1
35.77
1.01
10.36
32.94
8.60
5.28
0.07
b.d.l.
0.58
2.05
0.06
0.32
3.42
-0.13
100.3331.547
3.915
0.085

0.089
0.596
0.013
0.302

0.123
6.703
1.209
1.216
0.013
0.000
9.264

6.000
3.000

Březinapegmatite
76/1
35.53
0.97
10.29
33.68
8.56
4.83
0.09
b.d.l.
0.49
1.82
0.06
0.16
3.48
-0.07
99.89

31.226
3.840
0.160

0.013
0.594
0.011
0.382

0.035
6.873
1.802
0.339
0.026
0.024
9.099

6.000
3.000

Nosatá skála
pegmatite
12/1
35.64
0.28
10.32
34.64
12.80
1.35
0.18
0.19
0.07
1.82
0.05
0.30
3.42
-0.13
100.94

0.471
0.488
0.016
0.025
30.9073.672
0.328

30.878
3.564
0.436

0.146
5.356
2.672
0.966
0.047
0.000
9.187

6.000
3.000

30.554
3.689
0.311

0.151
0.781
0.025
0.043

0.130
5.331
2.923
0.537
0.097
0.000
9.018

6.000
3.000

Pegmatite
No. 12
45/1
104/1
33.60
34.13
1.09
0.98
9.73
9.89
25.45
25.73
17.89
19.88
3.63
2.05
0.31
0.65
b.d.l.
b.d.l.
2.46
0.80
1.41
2.29
0.07
0.11
0.58
0.56
3.08
3.15
-0.24
-0.24
99.06
99.98

0.179
0.659
0.018
0.144

0.038
6.214
2.241
0.630
0.031
0.000
9.154

6.000
3.000

Footwallgranite-pegmatite
36/1
34.80
0.29
10.08
30.58
15.54
2.45
0.21
b.d.l.
0.97
1.97
0.08
0.80
3.10
-0.34
100.5330.618
3.646
0.354

0.229
0.642
0.022
0.107

0.091
5.617
2.634
0.624
0.047
0.000
9.013

6.000
3.000

Pegmatite
No. 4
56/2
34.27
0.69
9.93
27.22
17.99
2.39
0.32
b.d.l.
1.22
1.89
0.10
0.64
3.12
-0.27
99.51

Tab. 4 Representative chemical compositions of tourmalines from granitic pegmatites in the Vlastějovice region (wt. % and apfu)

30.824
3.721
0.279

0.198
0.762
0.020
0.020

0.115
5.683
2.925
0.118
0.214
0.000
9.055

6.000
3.000

Spessartine
pegmatite
35/1
34.03
0.87
9.86
27.35
19.84
0.45
1.43
b.d.l.
1.05
2.23
0.09
0.50
3.16
-0.21
100.6530.263
3.749
0.251

0.340
0.608
0.025
0.027

0.156
4.806
3.227
0.512
0.097
0.000
8.798

6.000
3.000

X222
34.05
1.18
9.86
23.14
21.90
1.95
0.65
b.d.l.
1.80
1.78
0.11
0.45
3.19
-0.19
99.87

30.818
3.635
0.365

0.129
0.679
0.011
0.181

0.012
6.857
1.272
0.000
0.612
0.018
8.771

6.000
3.000

3010
35.31
0.09
10.23
34.24
8.95
b.d.l
4.25
0.14
0.71
2.06
0.05
0.68
3.21
-0.29
99.63

Elbaite pegmatite

30.556
3.543
0.457

0.198
0.680
0.006
0.116

0.002
7.332
0.040
0.000
0.929
0.000
8.303

6.000
3.000

4006
36.10
0.02
10.46
37.43
0.29
b.d.l.
6.60
b.d.l.
1.11
2.11
0.03
0.87
3.20
-0.37
97.85

Granitic pegmatites from Vlastějovice, the Moldanubian Zone

33

Milan Novák, Tomáš Kadlec, Petr Gadas

arsenopyrite, and pyrite are present in most pegmatite
bodies (Tab. 3). Fluorite as small violet grains andmasses occurs either in the more evolved Spessartine
pegmatite and Elbaite pegmatite but also in direct contact with the Fe-skarn in the primitive Pegmatite No.
12. Further details concerning the pegmatite (granite)dikes examined and review of all minerals identified
from the individual tourmaline-bearing pegmatite dikes
are given in Tab. 3.
Ackerman et al. (2007) inferred, based on the detailed
study of fluid inclusions and geological constraints (geothermal gradient, haplogranite solidus with 4.5 wt. %B2O3, feldspars thermometry), the following conditions
for the Elbaite pegmatite formation: P = 0.31–0.43 GPa,
T = 500–570 °C; the host-rock temperature during pegmatite emplacement was estimated at ~300 °C.

5. Chemical composition of minerals

5.1. Tourmaline
Tourmalines (schorl, dravite, foitite, elbaite, fluor-elbaite) from the individual types of pegmatites enclosed
in the orthogneiss, amphibole-bearing pegmatites hosted
by the Fe-skarn, and mainly tourmaline-bearing pegmatites cutting the paragneisses and Fe-skarn including
Footwall granite–pegmatite, differ significantly in theirchemical compositions (Tab. 4). Because tourmaline
forms fine-grained intergrowths with secondary Fe-richchlorite in all tourmaline-bearing pegmatites cutting the
Fe-skarn (Fig. 7a–b) except for the Elbaite pegmatiteand scarcely the Pegmatite No. 12 (Fig. 7c), determination of Fe2+/Fe3+ by Mössbauer spectroscopy (see e.g.,
Novák et al. 2011) was not possible. The individual
tourmaline grains are commonly slightly heterogeneous(Fig. 7c).

5.1.1. X-site
Two groups of tourmalines are evident in Fig. 8a, Ca-poor(Ca < 0.15 apfu, moderate to high proportion of vacancy
in the X-site) (Březina and Nosatá skála pegmatites cutting paragneisses, pegmatite in orthogneiss) and Ca-rich(Ca = 0.15–0.47 apfu, low to moderate X-site vacancy,X□ ≤ 0.25 pfu) (all pegmatites enclosed in the Fe-skarn,
including rare fibrous tourmaline from amphibole-bearing
pegmatite). Tourmaline compositions from the individual
dikes are scattered over a fairly large field (Fig. 8a).

5.1.2 Y-site and Z-site
Extremely high variability in Al contents of the individual tourmalines (Altot = 4.81–8.29 apfu) is the most typi34

cal feature. Pegmatites enclosed in the para- (Březina,
Nosatá skála) and orthogneisses, Footwall granite–
pegmatite and part of tourmaline (with high elbaite
component) from the Elbaite pegmatite (Fig. 8b) have
Altot greater than 6 apfu and thus they correspond to
ordinary tourmalines from granitic pegmatites (Selway
et al. 1999; Novák et al. 2004). Tourmalines from all
tourmaline-bearing pegmatites cutting the Fe-skarn and,rarely, the amphibole-bearing pegmatite are Al-poor,
including Spessartine pegmatite (5.20–5.59 apfu Al) andblack schorl from the Elbaite pegmatite (4.81–6.26 apfu
Al) (Fig. 8b). Tourmalines from pegmatites cutting the
Fe-skarn mostly having Altot < 6 indicate the presenceof Fe3+. The wet chemical analysis of schorl from the
Elbaite pegmatite showed elevated Fe 3+ of 0.54 apfu
(Povondra et al. 1985). Tourmalines from pegmatites
in para- and orthogneisses have clearly higher contentsof Mg (Mg/(Fe + Mg) = 0.22–0.52; Fig. 8b) than fromthe Footwall granite–pegmatite and primitive pegmatites
cutting the Fe-skarn (Pegmatites No. 12 and No. 4; Mg/(Fe + Mg) = 0.20–0.24). Tourmaline from orthogneiss
with Mg/(Fe + Mg) = 0.42–0.53 is the least fractionated. Evidently the most fractionated are the Spessartine
pegmatite and the Elbaite pegmatite ((Mg/(Fe + Mg) =0.07–0.10 and 0.00–0.16, respectively), whereby thevalues close to 0 are typical of elbaite and associatedschorl. Tourmaline from the Elbaite pegmatite (elbaite,
fluor-elbaite) is also significantly enriched in Mn (upto 0.31 apfu – wet chemical analyses of Povondra etal. 1985, or even 0.93 apfu Mn, electron microprobe
data; Tab. 4) as is common in elbaite-subtype pegmatites (Novák and Povondra 1995; Novák 2000; Novák
et al. 1999a, 2012). Low to moderate contents of Ti(0.03–0.16 apfu) are characteristic of tourmaline fromall examined pegmatites; slightly higher concentrationsof Ti were found in pegmatites enclosed in the Fe-skarn(Tab. 4). High surplus of Y + Z in most of analyses of
black tourmaline (Tab. 4) imply that the normalizationon the basis of 6 apfu Si and OH + F = 4 is not ideal
and that an oxy-tourmaline component is present alongwith Fe3+ and perhaps TAl (Povondra et al. 1985; Novák
et al. 2004; Bačík et al. 2013).

5.1.3. W-site
Concentrations of F vary from low in tourmalines fromthe pegmatites enclosed in para- and orthogneisses(0.01–0.21 apfu) to moderate in tourmaline-bearing
pegmatites cutting the Fe-skarn (0.24–0.37); the highest concentrations of F (0.31–0.46 apfu) were foundin the Footwall granite–pegmatite dike. Tourmalines
in the Elbaite pegmatite show much higher variationfrom 0.22 apfu F in black schorl to 0.56 apfu F in red
fluor-elbaite.

Granitic pegmatites from Vlastějovice, the Moldanubian Zone

(a)

(b)

Pl

Qz

(c)

(d)

Ab
Tur
Dsp
Ap

Qz
Ap

Ab
Kfs

(e)

(f)

Ep

Py

Ttn

Qz

Chl

Fig. 7 Back-scattered electron (BSE) images of selected minerals: a – euhedral tourmaline with secondary chlorite (bright) in dark plagioclase (Pl)from the Footwall granite–pegmatite; b – tourmaline (dark) with secondary chlorite (grey) and late titanite (bright veinlets), Březina pegmatite;c – zoned subhedral tourmaline (Tur) in association with quartz (Qz), albite (Ab), and apatite (Ap) from the Pegmatite No. 12; d – diaspore (Dsp)in albite (Ab) and quartz (Qz), in association with K-feldspar (Kfs) and apatite (Ap), Nosatá skála pegmatite; e – zoned titanite (Ttn) with Sn-rich
rim associated with epidote (Ep), Spessartine pegmatite; f – euhedral crystal of uraninite (bright) in quartz (Qz), see pyrite (Py) in chlorite rim(Chl), Spessartine pegmatite. Scale bar = 250 μm.

35Milan Novák, Tomáš Kadlec, Petr GadasXa)5.2. Biotite, muscovite
and chlorite

pegmatites fromorthogneiss
Amp-bearing pegmatiteBřezina pegmatite
Nosatá skála pegmatite
Footwall granite–
pegmatite
Pegmatite No. 12
Pegmatite No. 4
Spessartine pegmatite
Elbaite pegmatite

Ca

Na+K
Al

b)

Biotite is common to rare in all
pegmatite groups but typicallymore or less chloritized, especially in the tourmaline-bearing
pegmatites and thus a detailed
discussion of its chemistry is
not feasible. Biotite from all
pegmatites is Fe-rich showing
low variation in Mg/(Mg + Fe)(Fig. 9a) and is enriched in F
(0.08–0.42 apfu). Muscovites
from pegmatites cutting thepara- and orthogneisses are all
similar (Al = 2.74–2.91, Si =3.03–3.07, Fe = 0.04–0.08, Mg= 0.02–0.07 and F = 0.02–0.07
apfu). Also secondary chlorites
are Fe-rich; chamosite replacing
tourmaline in pegmatites fromthe Fe-skarn has Si = 2.58–
2.78 apfu and Mg/(Mg + Fe) =0.05–0.21, i.e. resembling the
replaced tourmaline. Secondary chamosite after biotite has
Mg/(Mg + Fe) = 0.01–0.35, i.e.
comparable with the precursor.
It differs from secondary chlorite after tourmaline by slightly
higher Si of 2.70–2.98 apfu.

5.3. Amphibole

foititeschorlFe50Al50

magnesio-foitite

draviteMg50Al50

Fig. 8 Compositional diagrams of tourmaline from granitic pegmatites in the Vlastějovice region:a – (Na+K) – vacancy in the X-site – Ca; b – Fe – Al – Mg.

36

Amphiboles from amphibolebearing pegmatites cutting the
Fe-skarn were examined indetail by Žáček and Povondra(1991) and Žáček (2007). Theyshow similar Mg/(Mg + Fe)of 0.13–0.25 in amphibolebearing pegmatites (hastingsite
to potassichastingsite; K ≤ 0.65
apfu and ≤ 3.15 wt. % K 2 O)
and of 0.11–0.29 in tourmaline-bearing pegmatites with
Footwall granite–pegmatite(potassian hastingsite with ≤0.4 K apfu and ≤ 1.77 wt. %K2O to potassian ferro-edenitewith ≤ 0.37 K apfu and ≤ 1.64
wt. % K2O; Fig. 9b). Contents

Granitic pegmatites from Vlastějovice, the Moldanubian Zone

Subhedral grains and their aggregates of brownish red andradite–grossular, up to 2 cm
in size, are typical of someamphibole-bearing pegmatites(Tab. 2). They are slightly
heterogeneous in composition(Fig. 10). Almandine-dominant garnets from both tourmaline-bearing pegmatites in
the paragneisses (Březina andNosatá skála) are only slightly
heterogeneous in the BSE images; garnet from the Březina
pegmatite is slightly enrichedin Mg and Ca (Fig. 10). By
comparison, spessartine-dominant garnet from the Spessartine pegmatite is evidently
enriched in Ca, Mn and Fe 3+(Fig. 10). Both the higher degree of fractionation expressedby higher Mn/(Mn + Fe) andstrong Ca,Fe-contamination
are recorded in this garnet. It
is also enriched in Y (up to
0.02 apfu, i.e. up to 0.41 wt. %Y2O3). Elevated contents of Y
were found only exceptionallyin Czech pegmatites (Hönig etal. 2010; Novák et al. 2012).

5.5. Feldspars

Amp-bearing pegmatites

eastonite

Nosatá skála pegmatite
Footwall granite–pegmatite

Mg/(Mg+Fetot)

5.4. Garneta) 1.0 phlogopite

Pegmatite No. 12
Spessartine pegmatite
Elbaite pegmatite

0.5

siderophyllite

annite

0.0
1.0

2.0

1.5

2.5

3.0

Al tot (apfu)b) 1.0

Amp-bearing pegmatites
Footwall granite–pegmatite
Pegmatite No. 12

Mg/(Mg+Fetot)of Si increase from 6.05 to
6.70 apfu, together with Mg/(Mg + Fe) (Fig. 9b). In the
tourmaline-bearing pegmatites,
hastingsite is typical of exocontacts and ferro-edenite of
endocontacts, respectively.

Pegmatite No. 4
Žáček (2007)

magnesiosadanagaite

edenitemagnesiohastingsite
0.5
hastingsitesadanagaite
ferro-edenite
0.0
4.5

5.0

5.5

6.0

6.5

7.0

7.5

Si (apfu)
Fig. 9 Compositional diagrams for biotite (a), and amphibole (b) (Leake et al. 1997) from granitic peg-

Composition of plagioclase matites in the Vlastějovice region. Amphibole analyses from ampfibole-bearing pegmatites taken from
(An0–32; see also Ackerman et Žáček and Povondra (1991) and Žáček (2007).
al. 2007) does not show any
No. 12 and up to An32 in the amphibole-bearing pegmaapparent differences among the individual pegmatite
tites. Compositions of perthitic K-feldspar vary fromtypes; in particular, high variation in Na/Ca is typical. For
almost pure KAlSi 3O 8 to Or 85Ab 15 and no significant
instance, plagioclase attains up to An15 in the pegmatites
differences were found among the individual pegmatitefrom the orthogneiss, An25 in the Březina pegmatite, An31
types, either.
in plagioclase associated with fluorite from the Pegmatite

37

Milan Novák, Tomáš Kadlec, Petr Gadas

Adr+GrsPrp

amp-bearing pegmatitesBřezina pegmatite
Nosatá skála pegmatite
Spessartine pegmatite

Alm

Sps

Alm

Sps

Fig. 10 Compositional diagrams of garnet from granitic pegmatites in the Vlastějovice region (mol. %).

5.6. Chemical composition of the selected
accessory minerals
Tourmaline-bearing pegmatites contain several accessory
minerals (see Tab. 3, Fig. 7d–f). Most of them apparently indicate an elevated degree of fractionation in theparental granitic rock. Empirical formulae of selectedminerals are given below. The Spessartine pegmatite contains several less common to very rare accessory phaseswith unusual compositions: Sn-rich titanite – Ca1.02(Ti0.61
Sn0.28Al0.09Fe0.04Nb0.01)1.03Si1.00O4.93F0.07 (Fig. 7e), Y-richmilarite – (K2.08Na0.04)2.12 (Ca2.24Y1.70Fe0.20Mn0.05)4.19Be4.00
Si24.85O59.84F0.16.H2O and mineral close to minasgeraisite(Y) – Ca0.84(Y0.66Fe0.35Yb0.09Er0.05)1.15Be2.0Si2.04O8(OH)0.89
F0.11 the latter two as inclusions in spessartine. In the
Elbaite pegmatite, “fluorcalciopyrochlore” (Ca1.14Na0.77
Sb0.01U0.01)1.93 (Nb1.40Ta0.52Sn0.07Ti0.01)2.00O6F1.17 and a secondary Bi-rich member of pyrochlore group (Bi0.78Ca0.36Fe0.33
Pb0.28Mn0.15Sb0.06U0.02)1.64 (Nb1.64Ta0.21Sn0.13Ti0.02W0.01)2.00O6
were found among the other accessory minerals (Tab. 3).
38

6. Discussion
The granitic pegmatites described from the Vlastějovice
region differ significantly in their mineral assemblages,
internal structure, host rocks and origin. Except for
those enclosed in the orthogneiss, the amphibole-bearing
pegmatites (various subtypes) were already described innumerous papers from Vlastějovice as well as from otherlocalities in the Moldanubian Zone (see Novák 2005;
Novák and Cempírek 2010 for review). We focused our
research on the pegmatites enclosed in the orthogneiss,amphibole-bearing pegmatites and, in particular, thetourmaline-bearing pegmatites (Tabs 2–3) to demonstrate
typical examples of various types of granitic pegmatites
in the Moldanubian Zone.

6.1. Pegmatites from orthogneisses
The granitic pegmatites enclosed in tourmaline-bearing
orthogneisses form rather small and uncomplicated bod-

Granitic pegmatites from Vlastějovice, the Moldanubian Zone

ies. Simple pegmatites from the Světlík orthogneiss (2.1
Ga; e.g., Wendt et al. 1993) were not studied in detailand they may represent the earliest granitic pegmatite
population in the Moldanubian Zone.
The parental orthogneisses to the simple pegmatites
distributed within the Varied Unit (Breiter et al. 2005a)
were dated as Ordovician (Hluboká nad Vltavou; Vrána
and Kröner 1995). Only localities Přibyslavice, Bechyně,Hamry nad Sázavou, and Vlastějovice were studied indetail and show rather distinct assemblages of accessory
minerals (e.g., tourmaline, fluorapatite, beryl, topaz,
löllingite, garnet – Hamry nad Sázavou; tourmaline,
fluorapatite, zircon, phenakite – Vlastějovice; Novák
1981; Staněk and Schnorrer 1983; Povondra et al. 1987;
Povondra 1989; Kadlec 2007a; Novák and Cempírek2010). They also show variable internal structure from
simply zoned elongated nests with rather sharp to slightly
diffuse contacts against the foliated host orthogneiss(Vlastějovice) to irregular coarse-grained facies of orthogneiss with transitional contacts and small pockets(Hamry nad Sázavou). However, lack of geological andmineralogical data from these pegmatites hinders a detailed discussion of their relations and origin.
The pegmatites occurring in the Přibyslavice orthogneiss body are more variable and only the most primitive
among them resemble the above localities in the simple
mineral assemblages (Novák and Cempírek 2010); however, primitive pegmatites were not studied in detail.
Apparently post-tectonic pegmatites with a variety ofminerals including Li-bearing ones (triphylite, Li-mica,
Li-tourmaline, amblygonite) and numerous accessory
minerals (see Povondra et al. 1987; Novák and Cempírek2010) are likely Variscan.

6.2. Amphibole-bearing pegmatites
Amphibole-bearing pegmatites, frequently with accessory
allanite and fluorite, cutting Fe-skarn bodies are relatively
common in the Moldanubian Zone (e.g., Rešice near
Hrotovice, Líšná near Svratka, Domanínek near Bystřice
nad Pernštejnem, Malešov near Kutná Hora; e.g., Němec
1963; Novák 2005; Novák and Cempírek 2010 and references therein). They exhibit simple internal structure(Fig. 3d) with dominant coarse-grained texture and locally with masses of quartz. At Vlastějovice, these masses
are randomly distributed in the pegmatite bodies and do
not resemble quartz core developed in many granitic
pegmatites. Also further textural–paragenetic units typical of granitic pegmatites such as graphic intergrowths ofquartz with K-feldspar or blocky K-feldspar are absent.
Their Ca–Fe ± F-rich mineral assemblages, concentrated
particularly along contacts of the pegmatite bodies (amphiboles, fluorite and allanite) (Fig. 4) and in pockets(prehnite, apophyllite) suggest strong but variable in situ

contamination from host Fe-skarn. In the studied pegmatites from Vlastějovice, Ca and Fe obviously come fromthe skarn; common allanite-(Ce) also suggests intake of
REE (Novák and Cempírek 2010). Fluorine was likely
derived from an early F-rich garnet (Grs 79–87And12–18;
F = 0.82–1.18 wt. %) preserved extensively as relics innewly-formed garnets (Grs12–52And40–71Alm2–14Sps0–2; F =0.10–0.25 wt. %), which originated during an early stageof MP–HT regional metamorphism of the host Fe-skarn(Žáček 1997; Žáček et al. 2003). Fluorine-rich garnet is
known also from other Fe-skarn localities in the Moldanubian Zone (Pertoldová et al. 2009; S. Houzar, pers.
comm. 2012). Ackerman et al. (2007) suggested, basedon the fluid inclusion study and feldspars thermometry,that the amphibole-bearing pegmatite crystallized at
0.42–0.58 GPa and 600–640 °C (Fig. 11). Such conditions are very similar to those for the regional metamorphism in the host Fe-skarn (0.45–0.65 GPa, 590–680 °C:Žáček 1997). This tectonometamorphic event very likely
generated rather primitive anatectic melts of the host
metapelitic rocks, which intruded the brittle Fe-skarn.
Absence of amphibole-bearing pegmatites in the hybrid
rock may suggest that the exchange reactions at the contact of the Fe-skarn and host gneisses and origin of theamphibole-bearing pegmatites (early stage of pegmatites
evolution) were rather simultaneous processes. However,high variability of amphibole-bearing pegmatites (shapeand size of pegmatite bodies, abundance and thickness ofreaction rims, presence/absence of pockets and proportions of the individual minerals) imply fairly variableconditions for their origin such as rheology and temperature of the host rock, and availability of fluids during
crystallization. Fluorite, an important accessory, minor
to exceptionally major mineral in the amphibole-bearing
pegmatites, crystallized during magmatic–hydrothermaltransition (Ackerman 2005).
The amphibole-bearing Magdalena pegmatite witha large pocket lined with crystals of smoky quartz andfeldspars differs from common pegmatites with pockets
lined with crystals of smoky quartz, tourmaline and feldspars occurring typically in the Strážek Moldanubicum(Gadas et al. 2012). Absence of pegmatite textures (e.g.,graphic intergrowths of Qz + Kfs) and B-rich minerals(tourmalines, dumortierite) is typical of all amphibolebearing pegmatites cutting Fe-skarn in the MoldanubianZone. Axinite and tourmaline are very rare or absent not
only in Vlastějovice but also at other localities (e.g., Filip
2002; Filip et al. 2006; Novák and Cempírek 2010). Consequently, although amphibole-bearing pegmatites andcommon pegmatites with smoky quartz and tourmaline
crystals in pockets are very likely anatectic in origin, theydiffer significantly in textures, chemical composition ofmelt (high B and Al in tourmaline-bearing pocket pegmatites) and mineralogy.
39

Mold
anu
Zone bian

Milan Novák, Tomáš Kadlec, Petr Gadas

0.2

o
e
Z
0

200

Ky d
An

ph
ibo
lite

lite

Am

a

f
b

d
c
e

1

20

10

l
Si d
An

lite

30

Gra
nu

0.4

te-am

his
t
eh p
r
P um
-P

ee
ns
c

0.6

Epido

B

0.8

0

2

phibo

s

e
lu

Gr

Pressure [GPa]

i
ch

lite

st

1.0

40

Depth [km]

1.2

400
600
Temperature [ C]

800

1000

Fig. 11 P–T path in metamorphic rocks of the Moldanubian Zone (modified from Pertoldová et al. 2009 using the P–T-data from Tajčmanová et al.
2007; Kotková 2007 and Schulmann et al. 2008, 2009). The position of the Al 2SiO5 triple point is from Pattison (1994), reaction 1: Alm + Als +Qz = Skn (sekaninaite) (Mukhopadhyay and Holdaway 1994); reaction 2: Crd + H 2O = Dsp (Hemley et al. 1980). The positions of the individual
pegmatites: a) borosilicates-bearing veinlet from the Bory Granulite Massif (Cempírek et al. 2010), b) amphibole-bearing pegmatites at Vlastějovice(Ackerman et al. 2007), c) common pegmatites with pockets from the Strážek Moldanubicum based on the data of Gadas et al. (2012), d) Elbaite
pegmatite at Vlastějovice (Ackerman et al. 2007), e) discordant rare-element pegmatites with primary sekaninaite, andalusite and diaspore fromthe Bory–Hatě area, Bory Granulite Massif; f) P–T data of the MP–HT metamorphism from the Fe-skarn (Žáček 1997).

6.3. Tourmaline-bearing granite–pegmatite
systemThe granite and pegmatite bodies occurring in the
Vlastějovice Fe-skarn represent a unique example of
granite–pegmatite system, where the individual small
pegmatite dikes show unambiguous relationship to thewell-defined parts of the texturally heterogeneous parental granite body (Figs 5, 6a–b, d). Both examined
tourmaline-bearing pegmatites from the paragneisses(Březina, Nosatá skála) were very likely related to thesame magmatic event as the granite–pegmatite systemcutting the Fe-skarn, although no explicit evidence isprovided.
The Footwall granite–pegmatite is highly heterogeneous showing textural evolution from medium- tocoarse-grained granite I, locally porphyritic (Tab. 1),

40

through subhomogeneous coarse-grained granite II tocoarse-grained granite III with large blocky K-feldspar
crystals (Fig. 6e). The texturally most primitive part of
the granite intrusion (granite I) generated rather irregularbody of the Pegmatite No. 12 with subhomogeneous internal structure built solely by a coarse-grained granitic
unit. Striking textural similarity with the granite I andbrecciated style of emplacement into the host Fe-skarn(Fig. 6a) suggest that the Pegmatite No. 12 rather represents an apophysis of the granite I with no clear evidence
for advanced fractionation. The more evolved Pegmatite
No. 4 was derived from the granite II (Fig. 6b); it forms ahomogeneous dike with a coarse-grained texture (Fig. 6c)resembling that of the parental granite II. The Spessartine
pegmatite with simply zoned internal structure including
graphic unit, rare blocky K-feldspars, minor albite unit
and small blocks of quartz, was derived from the mostGranitic pegmatites from Vlastějovice, the Moldanubian Zone

evolved granite III (Fig. 6d). Generally, the pegmatite
bodies cutting the Fe-skarn could be linked with thedifferent parts of the Footwall granite–pegmatite bodyand show apparent relationship: texturally more evolved
parental granite generated texturally and compositionallymore evolved pegmatite.
Different degrees of geochemical fractionation of
the individual pegmatite bodies are manifested by theirmineral assemblages (Tab. 3); e.g., increasing amountof tourmaline relative to biotite (or amphibole), or
presence of garnet in the Spessartine pegmatite andLi-bearing tourmaline in the most evolved Elbaite pegmatite. Clearly, also the amount of albite increases fromprimitive bodies in the paragneisses (Březina and Nosatá
skála pegmatites) and in the Fe-skarn (Pegmatite No. 12
and Pegmatite No. 4), through the Spessartine pegmatite
to the most evolved Elbaite pegmatite. The assemblagesof accessory minerals illustrate the increased degree offractionation in the Spessartine and Elbaite pegmatites as
well; e.g. ilmenite and Nb-rich rutile in the Spessartine
pegmatite and columbite and pyrochlore-group minerals
in the Elbaite pegmatite (see Tab. 3).
Different degrees of fractionation in the individual
pegmatite bodies are also evident from the chemicalcomposition of tourmalines (see Fig. 8a–b; Tab. 4), disregarding the overprint by Ca,Fe-contamination in thepegmatites cutting the Fe-skarn, where introduction of Fe
into tourmalines significantly decreased the Al contents
and Mg/(Mg + Fe) ratios. Slightly higher concentrationsof F in tourmaline (Tab. 4) from the pegmatites cutting
the Fe-skarn relative to the pegmatites from paragneisses
may be a product of contamination by the host Fe-skarn
indicated by abundance of fluorite in the more contaminated amphibole-bearing pegmatites (Žáček et al. 2003;
Ackerman 2005; Ackerman et al. 2007; Kadlec 2009;
Novák and Cempírek 2010). However, higher contentsof F in tourmaline may also be explained by crystal
structure, chiefly high Ca and low vacancy in the X-site(Novák 2000; Henry and Dutrow 2011). Moderate tohigh F concentrations in elbaite to fluor-elbaite (Tab. 4)very likely imply higher degree of fractionation of theparental pegmatite melt enriched in Li, Be, B, F, Mn, Nb
and Ta (see Tab. 3).
The field evidence from the tourmaline-bearing
pegmatites of the Vlastějovice region shows that the
body of Footwall granite–pegmatite was parental to all
tourmaline-bearing pegmatite dikes cutting the Fe-skarn(Figs 5, 11). The existence of a larger concealed granite
pluton, several km3 in size (see e.g, Baker 1998; London
2008), which would be related to this granite–pegmatite
system, is not supported by any field observations or
geophysical data. Intense mining works in the past also
confirmed a small size and regional extent of the Footwall granite–pegmatite (Koutek 1950). Such a granite

intrusion, however, is much smaller than is the size of
potential granitic plutons fertile to granitic pegmatites
commonly suggested (e.g., Černý 1991b; London 2008)
or even modeled (Baker 1998). Hence, the Vlastějovice
granite–pegmatite system is very unusual and raises thequestion, how granites parental to granitic pegmatites
may vary in their size, shape, textures, compositions andspatial relations (see e.g., Černý 1991b; Martin and De
Vito 2005; London 2008; Černý et al. 2012). Degrees oftextural differentiation and fractionation of the individual
tourmaline-bearing pegmatite dikes are comparable tothose of the respective parts of their parental granite intrusion. They are also related to the shape of pegmatite
bodies from an irregular brecciated Pegmatite no. 12 (Fig.
6a) to a thin and long dike of the evolved Spessartine
pegmatite (Fig. 6d). These are rather consistent with themodel of sequential derivation of pegmatite melts fromevolving parental granite (London 2008). However,parental granite intrusion is very small and this implies
thermal regime in its envelope different from large plutons. Thus the comparison between relatively voluminous
plutons (e.g., Černý 1991b) and small Footwall granite–
pegmatite body from Vlastějovice as fertile granites israther difficult.

6.4. Positions of granitic pegmatites in the
P–T space
The positions of the individual types of granitic pegmatites of the Moldanubian Zone in the P–T space (seeFig. 11) illustrate evident distinction between the Elbaite
pegmatite from Vlastějovice and other rare-element granitic pegmatites. The pressure of 0.31–0.43 GPa derived
from the fluid inclusion study (Ackerman et al. 2007) ishigher than that for the complex Moldanubian pegmatites,
where the presence of primary petalite (or spodumene
and quartz intergrowths after petalite), locally abundantandalusite and sekaninaite suggests pressures lower thanc. 0.2–0.3 GPa (Novák 2005; Novák and Cempírek 2010).
Whether it reflects different depth of pegmatite melt
emplacement in the Vlastějovice region relative to other(more southerly) parts of the Moldanubian Zone (Strážek
Moldanubicum, Jihlava region, Český Krumlov Unit) oroverestimation of the pressure for the Elbaite pegmatitefrom Vlastějovice (Ackerman et al. 2007) is not clear.
The Fig. 11 shows the estimated P–T conditions forvarious granitic pegmatites from the Moldanubian Zone.
It illustrates that primitive to highly evolved and typically B-rich pegmatites originated throughout much of
the Variscan evolution from the medium- (~0.6–0.7 GPa;
Cempírek et al. 2010) to the low-pressure conditions (lessthan 0.2 GPa in the Dolní Bory pegmatites, where common near end-member sekaninaite limits such low pressure). This trend is fairly consistent with the P–T paths
41

Milan Novák, Tomáš Kadlec, Petr Gadasof the Variscan metamorphism in the Moldanubian Zone
(Fig. 11) and indicates that formation of various granitic
pegmatites was an integral part of the tectono-magmatic
evolution of the region. Hence, granitic pegmatites andtheir minerals may be utilized in discussions of geological evolution of the region (e.g., Novák et al. 1998;
Novák 2001, 2005; Melleton et al. 2012).
Acknowledgements. The authors are very grateful to thereviewers R. Skála and P. Uher as well as handling editor
S. Vrána and editor-in-chief V. Janoušek for constructive
criticism that significantly improved the manuscript. We
are also indebted to S. Houzar for critical reading of themanuscript. This work was supported by the research
project GAČR P210/10/0743 to MN a PG.

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